Overview of Open Channel Flow - PowerPoint PPT Presentation

Overview of Open Channel Flow. Definition: Any flow with a free surface at atmospheric pressure Driven entirely by gravity Cross-section can vary with location and time, and is often irregular Examples Rivers, streams, natural channels Storm runoff, flood waves, tides, tsunamis

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l* is length in direction of flow, l is horizontal distance, z is distance in vertical direction from datum, y is vertical distance from bottom of channel, and q is angle that channel bottom makes with the horizontal.

HGL is always at water surface; designate slope of water surface as Sw.

EL is above HGL (i.e., water surface) by V2/2g. Slope of EL often referred to as the friction slope, Sf, or the energy slope, Se.

Bottom slope, So, equals sin q and is typically very small (~0.000118 on average for Mississippi R. from headwaters to mouth).

Because q is so small, land y are typically assumed to equal length along flow path and distance perpendicular to bottom, and sin qis approximately equal to tan q; those assumptions are made here. In this case, Sf = hL/l.

A length of channel under consideration, typically assumed to have constant q, is called a reach.

Steady flow refers to a flow pattern (y vs. l) that is constant over time; might or might not be constant over distance. We consider only steady flow here.

Steady flow can be uniform, gradually varying, or rapidly varying, which refer to the flow patterns over distance. In uniform flow, y is constant, so by continuity V is constant, and therefore Sw=Sf.

Along a cross-section perpendicular to streamlines (i.e., to channel bottom), pressure profile is hydrostatic, meaning z+(p/g) is constant. Strictly true only for parallel streamlines, but approximately true in gradually varying flow also.

Consider a shallow, stationary wave, generated by movement of bulk water downstream at the wave velocity c, as the wave moves upstream. System can be envisioned as the small ‘hump’ of water sliding upstream over the block of water flowing below it, generating a steady-flow scenario.

For a more general situation where the wave is not stationary, its net velocity relative to a stationary observer is c-V. If V<c, the net motion is in the direction of the wave, and if V>c, it is in the direction of the bulk flow. The ratio V/cis the Froude number, Fr, so for a surface wave:

If Fr<1, a wave propagates both upstream and downstream from its source and is ‘in hydraulic communication’ with upstream locations, and the flow is sub-critical. If Fr>1, the wave does not propagate upstream, and the flow is super-critical. If Fr=1, the flow is critical. The status of the flow in this regard has major implications for its behavior.

Previous plot fully describes width V vs. y, but it is sometimes convenient to show the same info in other ways. For instance, we could compare contributions of depth and velocity directly by expressing both in terms of head.

For certain analyses, it is useful to define the width specific energy, E, equal to y + V2/2g. E is actually head (not energy), and can be thought of as the energy of the water per unit weight, above and beyond that provided automatically by the terrain.

For water in a rectangular channel:

For a given q, E depends only on y. At low y, E is proportional to 1/y2, and at high y, E approaches y. Thus, E becomes large at low and high y, and passes through a minimum at intermediate y.